GEOLOGY OF THE LATE EOCENE CLARNO UNIT, JOHN DAY FOSSIL BEDS NATIONAL MONUMENT, CENTRAL OREGON

 

 

Erick A. Bestland and Gregory J. Retallack

Department of Geological Sciences

University of Oregon

Eugene, OR 97403

Theodore Fremd

John Day Fossil Beds National Monument

John Day, OR 97845

 

 

ABSTRACT

 

Through detailed stratigraphic section description and lithostratigraphic mapping in the type area of the Eocene Clarno Formation we have generated a geologic framework for the numerous fossil sites in the Clarno Unit of the John Day Fossil Beds National Monument. Two widespread conglomeratic units of andesitic composition are recognized in the area and are separated by red claystones (paleosols). The lower, conglomerates of the Palisades consists of channel and floodplain debris flow conglomerates and hyperconcentrated flood flow or lahar runout deposits. The overlying conglomerates of Hancock Canyon also contains channel and floodplain debris flow conglomerates, but has in addition fluvially reworked conglomerates and pebbly sandstones, reworked tuff beds, a distinctive amygdaloidal basalt flow and the "Nut Beds" fossil site. The Palisades unit is interpreted as a debris flow apron on which there was little lateral fluvial reworking. The Hancock Canyon unit is interpreted as a debris flow apron to a braidplain in an area of complex topography, with multiple sources of volcanic sediments. Above these two debris flow dominated units is the thick, but discontinuous, claystones of "Red Hill." These very clayey red beds record a long period of volcanic quiescence, slow floodplain aggradation and long periods of tropical and subtropical soil formation. A climatic change is inferred during the accumulation of the red beds from the presence of very strongly developed Ultisol-like paleosols in the lower half of the unit and well developed, Alfisol-like paleosols in the upper half. The changes between these two packages of paleosols may reflect climatic cooling and drying during late Eocene times. The overlying siltstones of the "Mammal Quarry" and associated andesite of Horse Mountain accumulated in response to renewed andesitic volcanism. The "Mammal Quarry" unit consists of tan and gray clayey sandy siltstones, gravel conglomerates and a basal andesitic breccia. The late Eocene mammal assemblage of the "Mammal Quarry" was preserved in a channel and floodplain sequence that accumulated rapidly in response to the eruption of the large and widespread flows of the andesite of Horse Mountain.

 

INTRODUCTION

The scenic high desert of north-central Oregon contains a colorful volcanic and alluvial sequence of Tertiary age. The combination of low precipitation (320 mm annually in Antelope) and seasonal temperature extremes (January mean of -1 oC and August mean of 19 oC; Ruffner, 1978) favors xerophytic, sparse vegetation and good exposures. In contrast, fossil flora of Eocene age from sites in the Clarno Unit indicate paratropical conditions analogous to that of modern southeast Asia (Manchester, 1981, in press). The transition from steamy jungles of the past to the open ranges of today is recorded in a copious fossil record of a diverse flora, invertebrates, freshwater fish, reptiles, and mammals in this region (Stearns, 1900; Stearns, 1906; Merriam and Sinclair, 1907; Dallas, 1920; Merriam and others, 1925; Chaney, 1925; Stirton, 1944; Scott, 1954; Downs, 1956; Cavender, 1968; Mellet, 1969; Naylor, 1979; Manchester, 1981; Wolfe, 1981a and 1981b; Ashwill, 1983; Martin, 1983; Rensberger, 1983; Manchester and Meyer, 1987; Hanson, 1989). These profound paleoenvironmental changes are also reflected in a sequences of paleosols ranging in age from middle Eocene to the present (Fisher, 1964; Retallack, 1981, 1991a, 1991b; Pratt, 1988; G.S. Smith, 1988). Three units of the John Day Fossil Beds National Monument (Sheep Rock, Clarno, and Painted Hills) were established for the protection and appreciation of these significant geologic and paleontologic resources.

This paper outlines geologic and paleoenvironmental findings of a three year study of the Clarno Unit. We describe new informal lithostratigraphic subdivisions of the Clarno Formation, with stratigraphic and paleoenvironmental data and preliminary interpretations. Data presented in this report were largely gathered from measuring and describing stratigraphic sections of outcrops, with extensive trenching to exposed fresh rock beneath badlands mantled with soil.

Basement rocks in north central Oregon consist of highly deformed metasediments of Permian age. In some areas, these are overlain by a thick sequence of Cretaceous marine rocks. In the Clarno area, phyllites and argillites of uncertain affinity (either Permian or weakly metamorphosed Cretaceous shales) are exposed in the Muddy Ranch dome. These basement rocks are intruded and overlain by andesitic volcanic and alluvial rocks of the Clarno Formation, which ranges in age from middle to late Eocene, some 54 to 37 my old (McKee, 1970; Enlows and Parker, 1972; Rogers and Novitsky-Evan, 1977; Manchester, 1981; Vance, 1988; Walker and Robinson, 1990). Volcanic plugs, lava flows, and lahars with convergent-margin andesitic compositions and textures indicate accumulation in and around andesitic volcanic cones of the Eocene Clarno volcanic arc (Noblett, 1981; Suayah and Rogers, 1991; White and Robinson, 1992).

Rhyolitic ash-flow tuff and dacitic to rhyodacitic tuffs are conspicuous in the latest Eocene, Oligocene, and early Miocene (22-to 39-my) John Day Formation (Peck, 1964; Woodburne and Robinson, 1977; Robinson and others, 1990; Bestland and others, 1993). These primary pyroclastic, alluvial and lacustrine deposits were supplied with volcanic ash from vents to the west in the present area of the Western Cascades (Robinson and others, 1984). Thus the Clarno and John Day formations of central Oregon record a late Eocene westward jump of the subduction zone in the Pacific Northwest and a corresponding change from Clarno andesitic volcanism to Cascade volcanism and John Day back-arc basin deposition.

The Clarno Unit-Hancock Field Station area can be divided into two areas based on structure: 1) relatively flat-lying strata of Horse Mountain, and 2) these same strata folded along a NE-SW fold limb. Other smaller folds are present in the area, however, the NE-SW fold dominates the local structure. This fold has the same orientation as the Muddy Ranch dome (Robinson, 1975), to the southwest of the project area. The fold dies out in the northeastern part of the project area (Fig. 1). In the Clarno Unit area, the geologic sequence is complicated by this NE-SW fold limb, intrusion of a dacitic dome, another small structural dome, and laterally variable volcanic facies.

 

STRATIGRAPHIC SUBDIVISIONS

Lower Clarno conglomerates. A sequence of boulder-sized, matrix-supported conglomerates exposed just to the west of Hancock Canyon is the oldest and most deformed unit in the mapped area. Its clasts are boulders and cobbles of altered plagioclase porphyritic andesite. The unit lacks tuff beds or paleosols and was recognized first by Hanson (1973). This unit forms the southwestern half of a structural dome. Another but less likely possibility is that this unit is part of the Palisades conglomerate unit that has been locally faulted and folded.

Hancock Dacite Dome. A plagioclase-hornblende porphyritic dacite body is exposed in the hills and gullies to the northeast of Hancock Field Station (Fig. 1). Excellent exposures of this unit in tributary gullies of Hancock Canyon indicate that it is a homogenous igneous body and not boulders of dacite weathering out of a debris flow. However, intrusive features such as baking, veining, alteration and mineralization of the surrounding country rock were not observed. Boulder deposits containing clasts exclusively of this dacite are present in well developed paleosols overlying the dacite. Thus the dacite body was an erosional feature that was mantled by colluvium and soils. The Hancock dacite dome is also pervasively altered, probably by deep weathering during the Eocene.

Main Sequence

In the study area, the Clarno Formation contains laterally extensive and mappable lithostratigraphic units (Fig. 1). The units are of two types: 1) andesitic debris flows and 2) andesite lava flows. Smaller-scale lithostratigraphic units, such as clayey red beds, basalt flows, and tuff beds are also present in this area (Fig. 2). These large debris flow and andesite flow units constitute the majority of the cliffs along the John Day River in the area south of Clarno bridge and along the western part of Pine Creek.

Andesite of Pine Creek. The base of the coherent section mentioned above consists of a thick andesite unit referred to as the andesite of Pine Creek. The unit consists of thick lava flows of dark-colored pyroxene-plagioclase andesite that are commonly altered by varying degrees. The unit has a very irregular upper surface which is mantled by a well developed reddish saprolite breccia. Pockets of red and white claystones are preserved between the andesite and overlying debris flows. The clayey saprolite and claystones erode to form an erosional bench which is occupied in part by the modern Pine Creek floodplain. Basal sapping of the overlying debris flows due to the erodability of these claystones is partly responsible for the Palisades cliffs. To the east of Cove Creek, the basal andesite unit is again extensively exposed. Thick, autobrecciated andesite flows are present beneath hill 2932 ("Dumbbell Hill") and include several basaltic andesite flows that onlap the highly porphyritic andesite and andesite breccia from the Dumbbell Section (Fig. 2).

Conglomerates of the Palisades. Onlapping the irregular surface of the andesite of Pine Creek is a thick sequence of matrix-supported andesitic debris flows. This unit has weathered into the spectacular hoodoos along Pine Creek and in the "West Face cliffs" along the John Day River (Fig. 1). Most of the debris flows are of the matrix-supported, moderately clast-rich floodplain debris-flow type (Scott, 1988). In the "Palisade cliffs," numerous clast-rich, channelized debris flows are present, some being clast supported at their base. Hyperconcentrated flood flow deposits (in the sense of G.A. Smith 1987; and Nemec and Muszynski, 1982) are also common. These grade into debris-flow deposits and occur as interbeds between debris flows. Well exposed at approximately the middle of the member are several thin, green, clayey paleosols with wood fragments and leaf impressions. These thin, green paleosols are present in the Palisades section and are well exposed in the lower part of the cliffs along the John Day River. Above the green clayey horizons is a tuffaceous breccia layer which grades up into a massive debris flow. This debris flow weathers brownish-orange and crops out prominently along the "West Face cliffs." To the east of Cove Creek, the Palisades unit debris flows onlap, thin and pinch-out against the andesite of Pine Creek (Figures 1 & 2).

Middle Clarno andesite. This thick andesite is locally present in the southern part of the project area along the John Day River south of Clarno bridge. The unit makes-up the lower half of the monolithic buttes on the west side of the John Day River (hills 2441 and 2373, Clarno 7.5 min. series) where the unit fills a paleovalley cut into the conglomerates of the Palisades on the west side of the river. The unit is onlapped by conglomerates of Hancock Canyon. It is a blocky, dark-colored, pyroxene-plagioclase andesite. Saprolite mantles the andesite and in places red claystones (paleosols) are present above this andesite. Where the andesite is absent, reddish claystones overlie the conglomerates of the Palisades. These claystones erode to form a bench on the mesa between Hancock Canyon and Indian Canyon (Indian Mesa on Fig. 1). This bench is also present on the north and west sides of Horse Mountain.

Conglomerates of Hancock Canyon. Overlying the red claystones at the top of the conglomerates of the Palisades is the conglomerates of Hancock Canyon. This unit includes tuffaceous beds and a distinctive basalt flow, but is dominated by matrix-supported boulder debris flows. The amygdaloidal, high silica basalt flow is laterally extensive, mappable, and stratigraphically in the upper half of the unit. The basalt is a holocrystalline, plagioclase and pyroxene basalt with common pahoehoe flow structures and local columnar jointing. The basalt can be mapped from the Hancock Field Station area to the Gables, is thickest in the "West Face cliffs," but is not present east of Indian Canyon.

The conglomerates of Hancock Canyon contain the "Nut Beds" fossil site and the Muddy Ranch Tuff, both dated at 44 Ma; C. Swisher obtained a date of 44 Ma from a plagioclase separate from a reworked crystal tuff in the "Nut Beds" using the 40Ar/39Ar method (pers. comm., 1992) and Vance (1988) obtained a date of 44 Ma from fission track of zircon crystals in the Muddy Ranch Tuff (also known as the Rajneesh Tuff) near the Gables. The Muddy Ranch tuff is stratigraphically below the "Nut Beds," also dated by Vance (1988) at 44 Ma. Many large, well-preserved Cercidiphyllum (katsura) and Macginitea (sycamore) permineralized tree trunks and limbs are in this unit, similar to the "fossil forests" found in comparably-aged Lamar River Formation on the Yellowstone plateau (Dorf, 1964).

Claystones of "Red Hill." In the Clarno Unit area, a thick sequence of reddish and grayish-purple claystones is present above the Hancock Canyon conglomerate unit. The unit is 59 meters thick in the "Red Hill" area (Fig. 2) but thins dramatically to the east (Fig. 1). In the cliffs on the west and north side of Horse Mountain, only a reddish saprolite with thin clay layer is present at this stratigraphic level. The unit at "Red Hill" contains a lower reddish paleosol sequence of very deeply weathered Ultisol-like paleosols and an upper less well developed, Alfisol-like paleosol sequence (G.S. Smith, 1988; Retallack, 1991a). A stony tuff bed divides the two paleosol sequences.

Andesite of Horse Mountain. This thick andesite unit is extensively exposed in the project area where it caps much of Horse Mountain. The unit consists of platy to blocky andesite which varies from pyroxene-plagioclase andesite to very porphyritic plagioclase dacite with traces of hornblende. Along the west and north side of Horse Mountain, the unit overlies a thick red saprolite developed on the amygdaloidal basalt flow in the Hancock Canyon unit. Ramp-like flow structures are common in lava flows exposed in the "West Face cliffs." The base of the unit dips gently to the west, probably following a paleoslope.

Siltstones of the "Mammal Quarry." The tan, clayey siltstones and cobble conglomerates of the Mammal Quarry beds are only locally present in the "Red Hill"-"Indian Canyon" area. A diverse vertebrate fauna has been excavated from the "Mammal Quarry," in the uppermost Clarno Formation below member A of the John Day Formation (Hanson, 1973 and pers. comm., 1993). Several taxa in this assemblage have close affinities with Asiatic faunas of the early Duchesnean North American Land Mammal Age. Pratt (1988) described Inceptisol-like paleosols from the "Mammal Quarry." By her interpretation, the fossil remains accumulated as carcasses and were disarticulated in a fluvial point bar. Stratigraphic work during this project has shown that the Mammal Quarry unit was deposited in response to the eruption of the andesite of Horse Mountain. At several exposures east of the "Mammal Quarry," red claystones of the Red Hill claystone unit are overlain by andesite breccia which can be traced to outcrops of andesite of Horse Mountain. This breccia grades into the tan clayey siltstones of the Mammal Quarry unit.

Welded tuff of member A. Rhyolitic pyroclastic volcanism of the John Day Formation is first recorded in north central Oregon by an ash-flow tuff re-dated at 39 Ma (Bestland et al., 1993). The John Day Formation in its western facies has been divided into informal members A-I based largely on the stratigraphy of ash flow tuff sheets (Peck, 1964; Swanson and Robinson, 1968; Robinson, 1975). The distinctive and widespread ash flow tuff of member A is very useful in delineating the Clarno surface at the onset of John Day volcanism.

Distinctive basalt flows and associated intrusions immediately overlie member A. They consist of aphanitic to sub-glassy basalt that weathers into cobble-sized blocks. These basalts correlate with the member B trachyandesites (Peck, 1964) well developed in the Ashwood area (Swanson, 1969), but also mapped in this area (Robinson, 1975).

 

DISCUSSION

The stratigraphic framework of these Clarno Formation lithostratigraphic units and corresponding fossil sites is complicated by rapid lateral stratigraphic changes. These changes are largely caused by erosional disconformities between units, original topography of many volcanic units, and local accumulation of some types of volcanic units (i.e. lava flows). Folding and faulting in the Clarno area and onlapping of the Hancock andesite dome have added to the local stratigraphic complexity. On a regional basis, the Clarno Formation remains largely undivided due to these factors as well as the lack of widespread Clarno marker beds.

The conglomerates of the Palisades are interpreted as a debris flow apron because they consist of debris flow deposits and largely lack reworked or fluvial interbeds. This Palisades debris flow apron was probably part of the constructional edifice of an active volcano. A volcanic apron to braidplain depositional setting is interpreted for the conglomerates of Hancock Canyon because they contain a variety of deposits including fluvial conglomerates, thin, reworked tuff beds, and matrix-supported debris flows. The variety of deposit types indicate a floodplain setting which received material from a variety of sources. Floodplain aggradation was largely controlled by volcanic eruptions and their corresponding debris flows. During volcanic hiatus there was fluvial reworking. On the earlier Palisades volcanic apron, in contrast, incision of the deposits predominated during volcanic hiatus thus giving rise to deeply nested channelized debris flows.

Within the Clarno area are numerous fossil plant localities (including several new sites, revealed during excavation for this study) that indicate apparently dissimilar climates. The classic "Nut Beds" site yields plant fossils strongly indicative of a tropical to paratropical climate (Manchester, 1981, in press). In contrast, at the same stratigraphic level and in a similar debris-flow depositional environment, the fossil plants found in Hancock Canyon suggest temperate conditions. These contrasting floral types are probably not different stages in ecological succession, because early successional fossil soils and plants are also found in this unit, and are dominated by horsetails and ferns. It is more likely that the "Nut Beds" flora represents a lowland rainforest, like the selva of tropical Mexico, whereas the Hancock Tree flora represents a higher altitude forest of cooler climatic affinities like the liquidambar oak forests of Mexico (Gomez-Pompa, 1973). Thus, according to this interpretation, the conglomerates of Hancock Canyon contain the ecotone between these two distinct forest types: an upland paratropical forest and a lowland tropical forest.

Deciduous forests of volcanic and other Eocene uplands were an important source of new plant communities as paleoclimate became cooler and drier from middle to late Eocene and then again in the early Oligocene (Wolfe, 1987). The vertebrate faunas also reflect these climatic shifts. Fossil mammals of the Clarno "Nut Beds" are comparable to the middle Eocene forest-dwelling faunas of much of North America. The "Mammal Quarry" fauna however, represents an immigration of new mammals from Asia, adapted to cooler and drier conditions. The Clarno volcanic arc provides some of the earliest evidence of these later faunas and may represent a staging area for the widespread North American faunas of the Chadronian NALMA (Retallack, 1991a).

 

ACKNOWLEDGEMENTS

Discussion and logistical support by Joseph and Connie Jones and Hancock Field Station staff are gratefully acknowledged. Helpful discussion with David Blackwell, Allan Kays, John Stimac and Paul Hammond has improved our understanding of the Clarno area. Critical reviews by Paul Hammond, Allan Kays, and Dave Blackwell have added to the clarity of this paper. This work was largely supported by the National Park Service and was initiated and completed with the support of the John Day Fossil Beds National Monument.

REFERENCES

Ashwill, M., 1983. Seven fossil floras in the rain shadow of the Cascade Mountains, Oregon: Oregon Geology, v. 45, p. 107-111.

Bestland, E.A., Retallack, G.J., Swisher, C.C.III, Fremd, T., 1993. Timing of cut-and-fill sequences in the John Day Formation (Eocene-Oligocene), Painted Hills area, central Oregon: Geological Society of America Abstracts with Programs, v. 25, p. 9.

Cavender, T.M., 1968. Freshwater fish remains from the Clarno Formation, Ochoco Mountains of north central Oregon: The Ore Bin, v. 30, p. 135-141.

Chaney, R.W., 1925. A comparative study of the Bridge Creek flora and the modern redwood forest: Contributions to Paleontology, Carnegie Institution Publication, 349 p.

Dallas, H.G., 1920. Fossil mollusks from the John Day Basin in Oregon: Oregon University Publication, no. 16, 8 p.

Dorf, E., 1964. The petrified forests of Yellowstone National Park: Scientific American, v. 210, p. 106-112.

Downs, T., 1956. The Mascall fauna from the Miocene of Oregon: Publications in Geological Sciences of the University of California, v. 31, p. 199-354.

Enlows, H.E., and Parker, D.J., 1972. Geochronology of the Clarno igneous activity in the Mitchell quadrangle, Wheeler county, Oregon: Ore Bin, v. 34, p. 104-110.

Fisher, R.V., 1964. Resurrected Oligocene hills, eastern Oregon: American Journal of Science, v. 262, p. 713-725.

Gomez-Pompa, A., 1973. Ecology of the vegetation of Veracruz; in Graham, A., ed., Vegetation and vegetational history of northern Latin America: Amsterdam, Elsevier, p. 73-148.

Hanson, C.B., 1973. Geology and vertebrate faunas in the type area of the Clarno Formation, Oregon: Abstracts and Programs of the Geological Society of America, v. 5, p. 50.

Hanson, C.B., 1989. Teletaceras radinskyi, a new primitive rhinocerotid from the late Eocene, Clarno Formation of Oregon, in D.R. Prothero and R.M. Schoch ed., The evolution of perissodactyls: Oxford University Press, New York, p.235-256.

Manchester, S.R., 1981. Fossil plants of the Eocene Clarno Nut Beds: Oregon Geology, v. 43, p. 75-86.

Manchester, S.R. and Meyer, H.W., 1987. Oligocene fossil plants of the John Day Formation, Fossil, Oregon: Oregon Geology, v. 49, p. 115-127.

Manchester, S.R., in press. Fruits and seeds of the middle Eocene Nut Beds flora, Clarno Formation, Oregon: Paleontographica Americana.

Martin, J.E., 1983. Additions to the early Hemphillian (Miocene) Rattlesnake fauna from central Oregon: Proceedings of the South Dakota Academy of Science, v. 62, p. 23-33.

McKee, T.M., 1970. Preliminary report on the fossil fruits and seeds from the mammal quarry of the lower Tertiary Clarno Formation, Oregon: The Ore Bin, v. 32, p. 117-132.

Mellet, J.S., 1969. A skull of Hemipsalodon (Mammalia, Deltatheridia) from the Clarno Formation of Oregon: American Museum Novitates, no. 2387, 19 p.

Merriam, J.C., and Sinclair, W.J., 1907. Tertiary faunas of the John Day region: Publications in Geological Sciences of the University of California, v. 5, p. 171-205.

Merriam, J.C., Stock, C. and Moody, C.L., 1925. The Pliocene Rattlesnake Formation and fauna of eastern Oregon, with notes on the geology of the Rattlesnake and Mascall deposits: Publications of the Carnegie Institute of Washington, v. 347, p. 43-92.

Naylor, B.G., 1979. A new species of Taricha (Caudata; Salamandridae), from the Oligocene John Day Formation of Oregon: Canadian Journal of Earth Science, v. 16, p. 970-973.

Nemec, W., and Muszynski, A., 1982. Volcaniclastic alluvial aprons in the Tertiary of Sofia district (Bulgaria): Annals of the Geological Society of Poland, v. 52, p. 239-303.

Noblett, J.B., 1981. Subduction-related origin of the volcanic rocks of the Eocene Clarno Formation near Cherry Creek, Oregon: Oregon Geology, v. 43, p. 91- 99.

Peck, D.L., 1964. Geologic reconnaissance of the Antelope-Ashwood area, north- central Oregon, with emphasis on the John Day Formation of late Oligocene and early Miocene age: U.S. Geological Survey Bulletin v. 1161-D, 26 p.

Pratt, J.A., 1988. Paleoenvironment of the Eocene/Oligocene Hancock mammal quarry, upper Clarno Formation, Oregon [MS thesis]: Department of Geological Sciences, University of Oregon, 104 p.

Rensberger, J.M., 1983. Successions of meniscomyine and allomyine rodents (Aplodontidae) in the Oligo-Miocene John Day Formation, Oregon: University of California Publications in Geological Science, no. 124, 157 p.

Retallack, G.J., 1981. Preliminary observations on fossil soils in the Clarno Formation (Eocene to early Oligocene) near Clarno, Oregon: Oregon Geology, v. 43, p. 147-150.

Retallack, G.J., 1991a. A field guide to mid-Tertiary paleosols and paleoclimatic changes in the high desert of central Oregon-Part I: Oregon Geology, v. 53, p. 51-59.

Retallack, G.J., 1991b, A field guide to mid-Tertiary paleosols and paleoclimatic changes in the high desert of central Oregon-Part II: Oregon Geology, v. 53, p. 61-66.

Robinson, P.T., 1975. Reconnaissance geologic map of the John Day Formation in the southwestern part of the Blue Mountains and adjacent areas, north-central Oregon: U.S. Geological Survey Miscellaneous Geological Investigations Map I- 872, 1:125,000.

Robinson, P.T., Brem, G.F., and McKee, E.H., 1984. John Day Formation of Oregon: a distal record of early Cascade volcanism: Geology, v. 12, p. 229-232.

Robinson, P.T., Walker, G.W., and McKee, E.H., 1990. Eocene(?), Oligocene and lower Miocene rocks of the Blue Mountains region, in G.W. Walker ed., Geology of the Blue Mountains region of Oregon, Idaho, and Washington: Cenozoic geology of the Blue Mountains region: U.S. Geological Survey Professional Paper, v.1437, p. 29-61.

Rogers, J.W. and J.M. Novitsky-Evans, 1977. The Clarno Formation of central Oregon, U.S.A.: volcanism on a thin continental margin: Earth and Planetary Science Letters, v.34, p. 56-66.

Ruffner, J.A., 1978. Climates of the states, volumes 1 and 2: Detroit, Gale Research, 1185 p.

Scott, K.M., 1988. Origins, behavior, and sedimentology of lahars and lahar-runout flows in the Toutle-Cowlitz river system: U.S. Geological Survey Professional Paper 1447-A, 74p.

Scott, R.A., 1954. Fossil fruits and seeds from the Eocene Clarno Formation of Oregon: Paleontographica, v. 396, pt. B, p. 66-97.

Smith, G.A., 1987. The influence of explosive volcanism on fluvial sedimentation: the Deschutes Formation (Neogene) in central Oregon: Journal of Sedimentary Petrology, v. 47, p. 613-629.

Smith, G.S., 1988. Paleoenvironmental reconstruction of Eocene fossil soils from the Clarno Formation in eastern Oregon [MS thesis]: Department of Geological Sciences, University of Oregon, Eugene, 167 p.

Stearns, R.E.C., 1900. Fossil land shells of the John Day region with notes on related living species: Proceedings Washington Academy of Science, v. II, p. 651-660.

Stearns, R.E.C., 1906. Fossil Mollusca from the John Day and Mascall beds of Oregon: University of California Publications, Bulletin of Department of Geology, v. 5, p. 67-70.

Stirton, R.A., 1944. A rhinoceros tooth from the Clarno Eocene of Oregon: Journal of Paleontology, v. 18, p. 265-267.

Suayah, I.B., and Rogers, J.J.W., 1991. Petrology of the lower Tertiary Clarno Formation in northcentral Oregon: the importance of magma mixing: Journal of Geophysical Research, v. 98, p. 13357-13371.

Swanson, D.A., 1969. Reconnaissance geologic map of the east hald of Bend quadrangle, Crook, Wheeler, Jefferson, Wasco, and Deschutes Counties, Oregon: U.S. Geological Survey Miscellaneous Geological Investigations Map I- 568, scale 1:250,000.

Swanson, D.A., and Robinson, P.T., 1968. Base of the John Day Formation near the Horse Heaven mining district, north-central Oregon: U.S. Geological Survey Professional Paper, 600D, p. 154-161.

Vance, J.A., 1988. New fission track and K-Ar ages from the Clarno Formation, Challis age volcanic rocks in north central Oregon: Abstracts of the Annual Meeting of the Rocky Mountain Section of the Geological Society of America, v. 20, p. 473.

Walker, G.W., and Robinson, P.T., 1990. Paleocene(?), Eocene and Oligocene(?) rocks of the Blue Mountains region of Oregon, Idaho and Washington: Cenozoic geology of the Blue Mountains region: U.S. Geological Survey, v. 1437, p.13-27.

White, J.D.L., and Robinson, P.T., 1992. Intra-arc sedimentation in a low-lying marginal arc, Eocene Clarno Formation, central Oregon: Sedimentary Geology, v. 80, p. 89-114.

Wolfe, J.A., 1981a. A chronologic framework for Cenozoic megafossil floras of northwestern North America and its relation to marine geochronology: in J.M. Armentrout, ed., Pacific Northwest biostratigraphy: Special Paper of the Geological Society of America, v. 184, p. 39-47.

Wolfe, J.A., 1981b. Paleoclimatic significance of the Oligocene and Neogene floras of the northwestern United States; in K.J. Niklas (editor), Paleobotany, Paleoecology and Evolution: New York, Praeger Publishers, p. 79-101.

Wolfe, J.A., 1987. An overview of the origins of the modern vegetation and flora of the northern Rocky Mountains: Annals of the Missouri Botanical Garden, v. 74, p. 785-803.

Woodburne, M.O., and Robinson, P.T., 1977. A new late Hemingfordian mammal fauna from the John Day Formation, Oregon, and its stratigraphic implications: Journal of Paleontology, v. 51, p. 750-757.

 

 

Figure 1. Geologic sketch map of the Clarno Formation from the John Day River near Clarno bridge and along Pine Creek. Quaternary landslide deposits have been omitted for clarity.

 

Figure 2. Stratigraphic fence diagram of the Clarno Formation.

Back to Table of Contents

United States Department of the Interior, National Park Service

Go to Nature Net Home Page Go to Park Net Home Page
Back to Table of Contents

United States Department of the Interior, National Park Service

Go to Nature Net Home Page Go to Park Net Home Page